indian journal of science and technology, vol 8(s3), 85–93

First report of Geochemical Characteristics of theSangan Manganese Occurrence,

Northeast Khash (Iran)Mahmoudreza Kahrazehi1*, Mohammad Lotfi1, Majid Ghaderi2,

Mohammad Mohajjel2 and Mohammadreza Jafari1

1Department of Geology, North Tehran Branch, Islamic Azad University, Tehran, Iran; [email protected]

2Department of Geology, Tarbiat Modares University, Tehran, Iran

AbstractThe Sangan manganese deposit is located 28 km northeast of the Khash city (Southeast of Taftan volcano) in the Sistan &Baluchistan province. Structurally and lithologically, this deposit lies in the central part of Iranian flysch zone. The ore body islayer in shape and lies above the Shale with intercalation meta sandstone - lithic tuffs of the Quaternary volcanic units contactand is completely hosted within dark gray to black lithic tuffs and in places interlinks with the dark gray to black lithic tuffs,so that the lithic tuffs play role keybed (line exploration) of manganese ore in the region. The geochemistry characteristicsof the Sangan deposit was studied by means of major oxide, trace and Rare Earth Element (REE) contents and the originof mineralization was discussed. The relatively high Al concentrations (5.95 to 7.22 wt.%, average = 6.61) in the ore ofSangan Mn deposit might result from lithic tuffs, which are the host rocks of the ore. Low titanium values (0.24 to 0.36 wt.%,average = 0.31) indicate limited clastic material entry during mineralization. In chondrite normalized REE graphics in all oresamples were characterized by slight negative Ce (0.10 to 0.11, average = 0.11) and negative Eu (0.18 to 0.22, average = 0.20)anomalies. The negative Ce anomaly was typical to hydrothermal deposits and negative Eu anomaly indicates contaminationfrom the continental crust and or sediment contribution via dehydration. The available data like; Mn:Fe (average 4.07),relatively high Ba (average 508,50), Co:Ni (average 0.18), Co:Zn (average 0.34), total REE (average 117.94), LREE > HREE,LREE:HREE (average 10.33), La:Ce (average 0.56), slight negative Ce and Eu anomalies and discrimination diagrams for Mndeposits indicated that the Sangan manganese deposit is hydrothermal type volcano-hydrothermal mineralization.

Keywords: Geochemistry, Hydrothermal, Iran, Khash, Manganese, Sangan

1. Introduction

A variety of features of manganese deposits, such asgeochemistry, distribution, composition, and theirformation environments are considered in many of pub-lications1. It is now generally understood that manganesedeposits have diverse origins. They can be formed byvarious processes, including sedimentary, hydrothermal,hydrogenous, and super gene. Hydrothermal manga-nese deposits are smaller than sedimentary manganesedeposits2. Hydrothermal manganese deposits are directlyprecipitated from low temperature hydrothermal solu-tions3. These deposits are generally of laminated andstrata bound or occur as irregular bodies and epithermal

veins. They are formed in different tectonic settings, suchas the marine environment next to spreading centers,intraplate seamounts, or in subduction related islandarc settings, and are found in both modern and ancientgeologic environments4,5. Hydrothermal deposits arecharacterized by high Mn:Fe content and low trace metalconcentrations6,7. Manganese and ferromanganese oredeposits are recognized with different ages and geologicsettings in Iran8. For example, the Infracambrian NariganMn ore deposit in Yazd province (Central Iran) has avolcano-exhalative genesis. The Cretaceous Benvid Mndeposit 35 Km south of Nain-Isfahan, with possible sedexgenesis and Kamar Talar Mn deposit in Sistan suturezone, East Iran9. There has been no detailed investigation

Indian Journal of Science and Technology, Vol 8(S3), 85–93, February 2015

*Author for correspondence

ISSN (Online) : 0974-5645ISSN (Print) : 0974-6846

DOI: 10.17485/ijst/2015/v8iS3/59884

First report of Geochemical Characteristics of the Sangan Manganese Occurrence, Northeast Khash (Iran)

Indian Journal of Science and TechnologyVol 8 (S3) | February 2015 | www.indjst.org86

powders under 200 meshes were analyzed at Kansaran Binaloud Laboratories, Tehran, Iran. Major oxide and trace element contents were determined with XRF and ICP-OES Respectively. REE’s were analyzed with ICP-MS method. Results of analysis are given in Tables 1, 2 and 3.

on the origin of the Mn mineralization from the Sangan area. Therefore, the purpose of this paper is to discuss field observations in conjunction with major, trace, and rare earth element (REE) geochemical data to constrain the genesis of Mn ore deposit in the Sangan region, Southeastern Iran.

2. Geological SettingThe Iran plate is part of northern margin of Gondwana which is separated from Eurasia by the paleotethys Ocean. The movement of bloks along folds and tectonic force are the main factors which played prominent roles in shap-ing the structural characteristics and geology of Iran. The Pressures and Strains to the Iran plate caused the region to be classified based on different theories in to several tec-tonic units10–15. The studied area is located in the central part of Iranian flysch zone. This zone is located between Lut Block to the west and Helmand (in Afghanistan) to the east. In contrast to Lut Block, the Flysch Zone is highly deformed and tectonized and consists of thick deep-sea sediments like argillaceous and silicic shales, radiolarite, and pelagic limestone and volcanic rocks such as basalt, spilitic basalt, diabase, andesite, dacite, rhyolite, and sub-ordinate serpentinized ultramafic rocks. The basement is likely composed of an oceanic crust. Most rock units in this zone fall into three main groups: 1- Flyschoid sediments, 2-Volcanic, volcano sedimentary and intrusive rocks 3-Ophiolitic series16. However there are some other names of this zone such as Nehbandan-khash zone17, Zabol-Baluch zone13, Flyschzone18 Sistan suture zone19, Iran East moun-tain20. The Sangan manganese Occurrence is Located 28 km Northeast of Khash city (Southeast of Taftan volcano) and 1 km West of Sangan village (N28-31-9.3, E61-15-42.3). Based on the Geological Map (1:1000 Scale), the Most Important Rock unites around deposit consists of gray to light green shale with intercalation meta sandstone, Dark gray to black lithic tuffs, white to milky ignimbrite tuffs and recent alluvium. Manganese Mineralization is associ-ated with dark gray to black lithic tuffs within Quaternary volcanic units (Figure 1 A, B and Figure 2).

3. Materials and Method 10 ore samples (~500 g each) were collected systematically from the Sangan manganese deposit. All this ore samples for geochemical analyses were taken representatively from the surface outcrop of ore beds in different locations. Samples

Figure 1. Satellite image (A) and Geographical position (B) of the study area in Southeastern Iran

Figure 2. Geological map (1:1000 scale) of the study area in Southeastern Iran.

Mahmoudreza Kahrazehi, Mohammad Lotfi, Majid Ghaderi, Mohammad Mohajjel and Mohammadreza Jafari

Indian Journal of Science and Technology 87Vol 8 (S3) | February 2015 | www.indjst.org

Tabl

e 1.

M

ajor

oxi

des (

wt.%

) of M

n-or

e in

the

stud

y ar

ea

Sam

ples

SiO

2A

l 2O3

Fe2O

3C

aON

a 2OK

2OM

gOTi

O2

P 2O5

MnO

L.O

.IM

nFe

Mn:

FeA

lTi

S 154

.25

11.5

22.

154.

742.

051.

651.

20.

430.

1812

.69

4.45

9.83

1.50

6.55

6.10

0.26

S 254

.31

13.6

55.

723.

061.

451.

751.

820.

600.

1914

.56

2.76

11.2

84

2.82

7.22

0.36

S 352

.54

12.3

53.

864.

852.

041.

621.

330.

520.

1813

.14

4.01

10.1

82.

73.

776.

540.

31

S 454

.32

12.7

64.

64.

982.

651.

731.

70.

570.

1910

.36

3.34

8.02

3.22

2.49

6.75

0.34

S 556

.11

12.6

54.

184.

582.

181.

681.

530.

530.

1810

.07

2.99

7.8

2.92

2.67

6.69

0.32

S 653

.52

11.2

42.

34.

842.

111.

611.

330.

400.

1713

.35

4.19

10.3

41.

616.

425.

950.

24

S 751

.54

12.3

43.

854.

82.

021.

591.

310.

480.

1714

.13

4.3

10.9

42.

694.

076.

530.

29

S 847

.83

13.6

5.52

3.6

2.3

2.2

1.57

0.59

0.85

13.5

5.12

10.4

63.

862.

717.

20.

35

S 946

.21

12.2

33.

633.

52.

12.

21.

250.

470.

8413

.16

5.1

10.1

92.

544.

016.

470.

28

S 1043

.84

12.5

3.04

3.1

1.5

1.6

1.4

0.54

0.72

14.1

66.

710

.97

2.13

5.15

6.62

0.32

Min

.43

.84

11.2

42.

153.

061.

51.

591.

20.

400.

1710

.07

2.76

7.8

1.50

2.49

5.95

0.24

Max

.56

.11

13.6

55.

724.

982.

652.

21.

820.

600.

8514

.56

6.7

11.2

84

6.55

7.22

0.36

Ave.

51.4

512

.48

3.89

4.21

2.04

1.76

1.44

0.51

0.37

12.9

14.

3010

2.72

4.07

6.61

0.31

Tabl

e 2.

Trac

e elem

ents

(ppm

) of M

n-or

e in

the s

tudy

area

Sam

ples

PbBa

CoG

aH

fN

bRb

SrTa

ThU

VW

ZrY

Mo

CuZn

Ni

AsTl

CsBe

Ge

Co:Z

nCo

:Ni

S 110

482

1620

.12.3

710

.178

.221

800.9

17.7

95.6

231

00.8

6015

58.2

1885

295

11.5

0.32.7

1.60.9

10.1

90.0

5

S 2 9

.856

048

19.8

2.71

1067

.522

000.9

37.9

14.3

846

91.1

6316

.369

.315

.285

.811

214

0.42.8

20.8

80.5

60.4

3

S 310

.148

416

.120

2.39

10.2

78.3

2200

0.97.8

15.6

431

30.9

6115

59.3

1985

.225

311

.80.3

2.81.7

0.93

0.19

0.06

S 413

.650

822

.820

2.97

13.9

73.2

1700

1.43

8.27

2.38

264

1.372

19.2

40.3

48.3

94.2

152

10.01

0.33.1

1.81.2

40.2

40.1

5

S 514

.345

818

.318

.42.8

912

.863

.515

401.0

27.8

3.43

252

174

18.3

41.2

32.9

88.3

150

100.3

2.81.7

0.87

0.21

0.12

S 6 9

.956

149

19.9

2.72

1167

.621

900.9

47.9

34.3

947

11.1

6416

.869

.515

.385

.929

114

0.42.8

2.10.8

90.5

70.1

7

S 715

.245

621

.820

.23.0

113

6921

601.2

17.7

62.8

640

61.1

7516

.855

.446

94.5

155

18.1

0.32.6

1.80.9

50.2

30.1

4

S 8 9

.855

947

19.7

2.69

1067

.521

800.9

37.9

24.3

836

91

6316

.769

.415

85.8

158

140.4

2.72.1

0.87

0.55

0.30

Min

. 9

.845

616

18.4

2.37

1063

.515

400.9

7.76

2.38

252

0.860

1540

.315

8511

210

0.32.6

1.60.8

70.1

90.0

5

Max

.15

.256

049

20.2

3.01

13.9

78.3

2200

1.43

8.27

5.64

471

1.375

19.2

69.5

48.3

94.5

295

18.1

0.43.1

2.11.2

40.5

70.4

3

Ave.

11.59

508.5

029

.8819

.762.7

211

.3870

.6020

441.0

37.9

04.1

435

71.0

466

.5016

.7657

.8326

.2188

.0919

612

.930.3

42.7

91.8

50.9

40.3

40.1

8



4. Results and Discussion

4.1 Field ObservationsThe ore body in the study area is layer in shape. The ore body lies above the Shale with intercalation meta sand-stone-lithic tuffs contact and is completely hosted within dark gray to black lithic tuffs and in places interlinks with the dark gray to black lithic tuffs, so that the lithic tuffs play role keybed (line exploration) of manganese ore in the region. Wherever we have this rock unit (lithic tuffs), manganese mineralization could be observed as scattered grains in the space between ashes and pyroclastic particles. But, these pyroclastic particles have been crashed in some places and there have been some fine fractures between them that they are also filled with manganese oxide ores result from volcanic activities. The ore layers generally vary in thickness from 1 to 2 m, in length from 400 to 800 m and wide from 4 to 8 m. The ore trends approximately east-west to northwest-southeast and dips southeast between 20° and 25°. Ore has been exploited mainly by small-scale miners using rudimentary methods at Sangan (Figure 3).

Tabl

e 3.

RE

E co

ncen

trat

ions

of o

re sa

mpl

es (p

pm) i

n th

e D

ehoo

man

gane

se o

ccur

renc

e

Sam

ple

LaC

ePr

Nd

SmEu

Gd

TbD

yH

oEr

TmYb

LuY

ΣREE

ΣLRE

EΣH

REE

LREE

:HRE

ELa

:Ce

Ce:

Ce*

Eu:E

u*

S 125

.544

5.31

20.4

3.45

1.07

3.42

0.45

2.45

0.55

1.3

0.24

0.25

0.25

1510

8.64

99.7

38.

9111

.19

0.58

0.11

0.22

S 227

.746

5.94

223.

911.

073.

780.

542.

860.

621.

630.

310.

260.

2716

.311

6.89

106.

6210

.27

10.3

80.

600.

100.

20

S 325

.345

.15.

3220

.53.

461.

083.

440.

472.

520.

561.

40.

260.

230.

2415

109.

8810

0.76

9.12

11.0

50.

560.

110.

22

S 427

.553

.66.

4625

.24.

751.

194.

420.

683.

540.

761.

940.

340.

250.

3119

.213

0.94

118.

712

.24

9.70

0.51

0.11

0.18

S 525

.850

.16.

0623

.74.

551.

154.

050.

633.

360.

721.

890.

330.

270.

318

.312

2.91

111.

3611

.55

9.64

0.51

0.11

0.18

S 627

.847

5.95

22.2

3.81

1.08

3.79

0.54

2.87

0.63

1.64

0.3

0.26

0.27

16.8

118.

1410

7.84

10.3

10.4

70.

590.

100.

20

S 725

.349

.25.

9523

.34.

421.

153.

960.

613.

210.

691.

810.

30.

240.

2716

.812

0.41

109.

3211

.09

9.86

0.51

0.11

0.19

S 827

.645

5.94

22.1

3.8

1.07

3.77

0.53

2.85

0.61

1.62

0.3

0.26

0.26

16.7

115.

7110

5.51

10.2

10.3

40.

610.

100.

20

Min

.25

.344

5.31

20.4

3.45

1.07

3.42

0.45

2.45

0.55

1.3

0.24

0.23

0.24

1510

8.64

99.7

38.

919.

640.

510.

100.

18

Max

.27

.853

.66.

4625

.24.

751.

194.

420.

683.

360.

761.

940.

340.

270.

3119

.213

0.94

118.

712

.24

11.1

90.

610.

110.

22

Ave.

26.5

647

.50

5.87

22.4

34.

021.

113.

830.

562.

960.

641.

650.

300.

250.

2716

.76

117.

9410

7.48

10.4

610

.33

0.56

0.11

0.20

Figure 3. General lithological column of the study area in Southeastern Iran.

11

Figure 3. General lithological column of the study area in Southeastern Iran.



4.2 Major and Trace Elements Geochemistry Geochemical criteria to distinguish ferromanganese deposits of various origins are well established. Major element ratios, trace element concentrations have been widely used to assess the origin of manganese deposits21–23. Among the major oxides, Mn, Fe, Ti and Al contents are very useful to delineate the origin of manganese ores23,24. Many authors use Mn:Fe ratio as discrimination genetic factor between manganese deposits; for example; this ratio in lacustrine deposits is (Mn:Fe< 1), hydrogenous (Mn:Fe = 1) and Sedex deposits (0.1 <Mn:Fe< 10)25. Analytical results of the major and trace elements of the Sangan Mn deposit are given in Tables 1 and 2. Mn concentration ranges from 7.8 to 11.28 wt.% (average = 10), and Fe ranges from1.50 to 4 wt.% (average = 2.72) in the Sangan Mn deposit. Mn:Fe ratios of the deposit are 2.49–6.55 (average = 4.07) (Table 1). These values are rela-tively conformable with those of hydrothermal manganese deposits. Like Fe and Mn contents, Aluminium and Titanium concentrations are used for the identification of manganese mineralization, and Al is generally related to clay minerals in the sediments26. Ti is immobile in hydrothermal solutions and as such is measure of clastic input21,27,28. The relatively high concentrations of Al values in Mn oxide deposits also suggest a significant sedimen-tary contribution during precipitation29. Al concentrations of ore samples in the Sangan deposit range from 5.95 to 7.22 wt.% (average = 6.61), and Ti concentrations range from 0.24 to 0.36 wt.% (average = 0.31) (Table 1). The relatively high Al concentrations in the ore of Sangan Mn deposit might result from lithic tuffs, which are the host rocks of the ore. Low titanium values indicate limited clastic material entry during mineralization.

The hydrogenous and hydrothermal deposits can be distinguished by using Co:Ni and Co:Zn ratios30. A ratio of Co:Ni< 1 and Co:Ni> 1 indicates a sedimentary origin and a deep marine environment, respectively28,31–33. Co:Ni ratio in the Sangan Mn deposit range from 0.05 to 0.43 (average = 0.18) (Table 2). Co:Zn ratio of 0.15 indi-cates hydrothermal type deposits, while Co:Zn ratio of 2.5 indicates hydrogenous type deposits30. Co:Zn ratio in the Sangan Mn deposit range from 0.19 to 0.57 (aver-age = 0.34) (Table 2). Although Co:Zn ratio from the Sangan Mn deposit point to a hydrothermal source for Mn mineralization, Co:Ni ratio of ore samples indicate that sedimentary environments played an important role during the formation of the Mn deposit.

Ba concentrations in hydrothermal solutions are higher than seawater because of the influence of volcanic activity and sedimentation28,33,34. Ba concentrations in the Sangan manganese deposit range from 456 to 560 ppm (average = 508.50) reflecting in general, the characteristics of hydrothermal deposits.

Different major and trace element discrimination diagrams have been proposed by many workers to dis-tinguish manganese ores of various origins26,29,30,35–41. These discrimination diagrams have been used to distin-guish between a hydrothermal (continental or marine) and a hydrogenous origin. The term hydrothermal refers to manganese oxides deposited directly from geother-mal waters around hot springs and pools in continental environments or sedimentary-exhalative manganese mineralization deposited in marine environments38. The term hydrogenous refers to deposits formed by slow pre-cipitation or adsorption of dissolved components from sea water26,36,38. The Si vs. Al binary diagram30, 39, the Mn-Fe-(Co + Ni + Cu) × 10 triangular diagram26,36,41, the Zn-Ni-Co triangular diagram29, the Co:Zn vs. Co + Ni + Cu diagram30, and the Co + Ni vs. As + Mo + V + Cu + Pb + Zn diagram37 are used in this study to discriminate between the hydrothermal and hydrogenous character of the deposit.

All the studied manganese ore samples in triangular (Figure 4B and C) and binary (Figure 4A, D and E) dis-crimination diagrams plot within the hydrothermal field. Trace element concentrations in the manganese oxides show the mostly hydrothermal origin for manganese deposit in the Sangan region (Table 2; Figure 4A to E).

4.3 Rare Earth Elements GeochemistryMajor oxide, trace and REE geochemistry are very useful for understanding the formation conditions of ore deposit. REE contents of 8 ore samples collected from the Sangan manganese deposit are listed in Table 3. Hydrothermal deposits show relatively low REE, but hydrogenous depos-its have a significantly higher amount28,42–44. The total REE (ΣREE) concentrations of Sangan Mn ore range from 108.64 to 130.94 ppm (average = 117.94) (Table 3), the low contents of REE composition of studied ore samples are conformable with hydrothermal manganese deposits23,45. Total light REE: heavy REE (i.e., ΣLREE:ΣHREE) and La:Ce ratios of the Sangan Mn ore given in Table 3, can be used as an indicator of primary enrichment during the Mn oxidation processes28,33,46. LREE > HREE value may indicate mineralization related to hydrothermal



solutions28,33,47. The total LREE: total HREE ratio ranges from 9.64 to 11.19 (average = 10.33) in the Sangan Mn ore. These values indicate that hydrothermal solutions played an important role in the formation of Sangan Mn deposit. Hydrothermal crusts have La:Ce ratios similar to seawa-ter (~2.8), but hydrogenous Mn-Fe crusts have a much lower La:Ce ratio (~0.25)48. La:Ce ratio for the Sangan Mn ore vary between 0.51 and 0.61 (average 0.56) (Table 3 and Figure 5). This ratio suggests a major input from a hydrothermal source for the Sangan Mn ore Figure 5.

Although the relationship between manganese deposits and their REE distribution has been studied49–52, there is no generally accepted model for reflecting the deposit type (e.g., hydrothermal, diaganetic, hydroge-netic) and oxidative and reductive deposition conditions. Ce and Eu, the two most important REEs, are commonly used for the prediction of fluid source and redox potential of the environment. Ce and Eu anomalies are defined as Ce:Ce* = [(Cen):(Lan×Prn)1/2 and Eu:Eu* =

[(Eun):(Smn×Gdn)1/2, respectively, where Ce* and Eu* are the hypothetical concentrations53. The subscript “n” indicates chondrite-normalized values54.

Slight negative Ce anomalies are considered as an indicator of volcanogenic input55 or hydrothermal con-tributions to seawater50,51, whereas a strong negative Ce anomaly is characteristic of low temperature hydrother-mal deposits around the hot spots in mid-ocean and island arc spreading centers56,57.

Positive Ce anomalies are characteristic for modern seafloor oxyhydroxide deposits and nodules58. A negative Ce anomaly is observed in all ore samples taken from the Sangan Mn ore (Table 3). Ce:Ce* anomaly values range between 0.10 and 0.11 (average = 0.11) a range which is similar to low temperature hydrothermal deposits.

A positive Eu anomaly in hydrothermal deposits sug-gests high temperature hydrothermal fluids59 and reflects the interaction of heated waters with substrate volcanic rocks of high Eu content during circulation60. A negative Eu anomaly indicates an insufficient interaction of ground water with substrate volcanic rocks due to low tempera-ture60 and contamination from the continental crust and or sediment contribution via dehydration28,33,61.

A negative Eu anomaly is found in all the manganese samples taken from the Sangan Mn ore (Table 3). Eu:Eu* anomaly values range from 0.18 to 0.22 (average = 0.20). This suggests a low temperature hydrothermal solution, which affected mineralization. We conclude that REE patterns of the Sangan manganese deposit are generally similar to those from hydrothermal manganese deposits. All the studied ore samples shows light negative Ce and negative Eu anomalies (Figure 6).

REE patterns of the region (Figure 6) are compared with those of hydrothermal and hydrogenous manganese deposits (Figure 7). Results indicate that hydrogenous

Figure 4. Discrimination diagrams for manganese deposits. (A) Si vs. Al discrimination diagram30,39, (B) Mn–Fe–(Ni + Co + Cu)x10 discrimination diagram26,36,41, (C) Zn–Ni–Co discrimination diagram29, (D) Co:Zn–Co + Ni + Cu discrimination diagram30 and (E) Co + Ni vs. As + Mo + V + Cu + Pb + Zn discrimination diagram37.

Figure 5. Plot of Sangan Mn ore on the La vs. Ce discrimination diagram30,48.



manganese deposits are more enriched in REE’s than their hydrothermal equivalents and hydrogenous man-ganese deposits are represented by positive Ce anomaly, but hydrothermal deposits are characterized by negative Ce anomalies3,62. Ore samples of the Sangan manganese deposit show slight negative Ce anomalies which resem-ble the pattern of hydrothermal deposits (Figure 6). Eu shows negative anomaly in all ore samples indicating con-tamination from the continental crust and or sediment contribution via dehydration33,61.

5. ConclusionsThe Sangan manganese deposit is associated with Dark gray to black lithic tuffs within Quaternary volcanic units at 28 km Northeast of Khash city (Southeast of Taftan volcano) and 1 km West of Sangan village (N28-31-9.3, E61-15-42.3). Major oxide, trace and REE element assess-ment show that hydrothermal activities were effective for

the formation of the Sangan manganese deposit. Also, the studies reveal that mineralization of manganese in layered form and strati form and related to Dark gray to black lithic tuffs with quaternary age, which is generally conformable with bedding host rock (lithic tuffs). The contacts with the tuffs are suddenly and associated with pyroclastic-volcanic activities of Taftan volcano. They have been formed as the horizontal layers and placed on the middle Eocene folded flysches unconformably. Therefore, it can be concluded that both volcanic and hydrother-mal conditions were caused in the formation of Sangan manganese deposit which may be described as related to volcano-hydrothermal occurrence. It seems that hydro-thermal fluids and volatile materials with high hydraulic pressure and explosively are ejected and exited from a fur-ther volcanic source related to Taftan Volcanism and have passed distance due to the low density and gradually have been deposited as horizontally and unconformably on the middle Eocene flysches. The question is why they have been found in only one horizon and contaminated with manganese oxides. Manganese along with other materials such as volcanic ashes and pyroclastic fragments during the exit of the volcanic channel do not react with oxy-gen at the same time, because Manganese has low ionic potential, it takes a short time, which coincided with an explosion of volcanic ashes and pyroclastic fragments and finally it’s deposition. In the case of fine-grained mate-rial impregnated with manganese oxy-hydroxides are deposited with volcanic ashes and angular fragments of pyroclastic simultaneously, and finally, they have made a cycle of manganese mineralization horizontally.

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